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Causes and Timing of Future Biosphere Extinctions

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Causes and Timing of Future Biosphere Extinctions Biogeosciences, 3, 85–92, 2006 www.biogeosciences.net/3/85/2006/ Biogeosciences © Author(s) 2006. This work is licensed under a Creative Commons License. Causes and timing of future biosphere extinctions S. Franck, C. Bounama, and W. von Bloh Potsdam Institute for Climate Impact Research, Potsdam, Germany Received: 28 September 2005 – Published in Biogeosciences Discuss.: 7 November 2005 Revised: 25 January 2006 – Accepted: 26 January 2006 – Published: 10 March 2006 Abstract. We present a minimal model for the global carbon boiling-point of water. Within the framework of Earth sys- cycle of the Earth containing the reservoirs mantle, ocean tem science (Franck et al., 2000, 2002) our planet is de- floor, continental crust, biosphere, and the kerogen, as well scribed as a system of certain interacting components (man- as the combined ocean and atmosphere reservoir. The model tle, oceanic crust, continental lithosphere, atmosphere, hy- is specified by introducing three different types of biosphere: drosphere, and biosphere) that develops under increasing procaryotes, eucaryotes, and complex multicellular life. Dur- external forcing (increasing insolation) and changing inter- ing the entire existence of the biosphere procaryotes are al- nal forcing (decreasing spreading rate, growing continen- ways present. 2 Gyr ago eucaryotic life first appears. The tal area). Within certain limits the Earth system is able to emergence of complex multicellular life is connected with an self-regulate against changing external and internal forcing. explosive increase in biomass and a strong decrease in Cam- The life span of the biosphere is related to these limits of brian global surface temperature at about 0.54 Gyr ago. In self-regulation. Lovelock and Whitfield (1982) published the long-term future the three types of biosphere will die out the first estimations of the biosphere’s life span. Accord- in reverse sequence of their appearance. We show that there ing to their semi-quantitative model, photosynthesis ceases is no evidence for an implosion-like extinction in contrast to already in about 100 Myr because the atmospheric carbon the Cambrian explosion. In dependence of their temperature dioxide content falls below the minimum value for C3-plants tolerance complex multicellular life and eucaryotes become (150 ppm). The first quantitative model for the long-term fu- extinct in about 0.8–1.2 Gyr and 1.3–1.5 Gyr, respectively. ture of the biosphere was proposed by Caldeira and Kast- The ultimate life span of the biosphere is defined by the ex- ing (1992). With the help of a more sensitive climate model tinction of procaryotes in about 1.6 Gyr. and under the assumption of a minimum atmospheric CO2 value of 10 ppm for C4-plants, they calculated that the bio- sphere’s life span extends up to about 800 Myr. Franck et al. (2000) developed an Earth system model that takes into 1 Introduction account quantitatively the internal forcing by geodynamics. The general basis of this paper is the long-term evolution of This effect results in a reduction of the biosphere life span the global carbon cycle from the Archaean up to about 2 Gyr from 800 Myr to 600 Myr. The biotic enhancement of weath- into the future and its consequences for the Earth’s climate ering and its influence on the life span was investigated by and the biosphere. In particular, we investigate the influ- Lenton and von Bloh (2001). According to their results the ence of geosphere-biosphere interactions on the life span of current biosphere should remain resilient to carbon cycle per- the biosphere. The problem of the long-term existence of turbation or mass extinction events for at least 800 Myr and the biosphere was first discussed by astrophysicists. They may survive for up to 1.2 Gyr. The question of the life span analysed increase of insolation during Sun’s evolution on the of the biosphere is also connected to the question of the fate main sequence. Already in the 1960s, Unsold¨ (1967) pre- of the Earth’s ocean. Bounama et al. (2001) have shown that dicted the ultimate end of terrestrial life in about 3.5 Gyr liquid water will be always available in the surface reservoirs when solar luminosity will be about 40% higher than now as a result of internal processes. The extinction of the bio- and temperatures at the Earth’s surface will be above the sphere will not be caused by the catastrophic loss of water but by other limiting factors caused by the external forcing Correspondence to: C. Bounama of increasing solar luminosity. ([email protected]) Published by Copernicus GmbH on behalf of the European Geosciences Union. 86 S. Franck et al.: Causes and timing of future biosphere extinctions dC All these estimations of the biosphere life span deal with f = + − −1 Fprec Co+a,Cc Fhyd τf Cf (4) a rather simple unique biosphere existing within a certain dt temperature tolerance window and above a certain minimum value of atmospheric CO2 content. A natural extension to dCbio,1 −1 = 5 (Co+a) − τ C a more specific biosphere is to introduce three types of bio- dt 1 bio,1 bio,1 sphere (procaryotes, eucaryotes, complex multicellular life) . with different temperature tolerance windows and different . (5.1...5.n) biotic enhancement of weathering. According to Ward and dCbio,n −1 = 5n (Co+a) − τ C Brownlee (2002) the long-term future of the biosphere is in dt bio,n bio,n some sense a mirror image of the history: the different bio- sphere types will become extinct in reverse sequence of their n appearance. dCker X −1 −1 = γ τ C ,i − τ C (6) In the present paper we apply our general model for the dt bio,i bio ker ker i=1 long-term co-evolution of the geosphere and the biosphere (Franck et al., 2002) with three different biosphere pools The variable t is the time, τf the residence time of carbon in (procaryotes, simple eucaryotes, and complex multicellular the seafloor, A the accretion ratio of carbon, R the regassing life) to investigate the long-term evolution of the biosphere. ratio, SA the areal spreading rate, fc the degassing fraction Our model was previously used to investigate the Cam- of carbon, dm the melt generation depth, Vm the mantle vol- brian explosion as triggered by geosphere-biosphere feed- ume, Fweath the weathering rate, Fprec the rate of carbonate backs (von Bloh et al., 2003). We found that the Cam- precipitation, Fhyd the hydrothermal flux, γ the fraction of brian explosion was mainly driven by extrinsic environmen- dead biomass transferred to the kerogen, τbio,i the residence tal causes and so rapid because of a positive feedback be- time of carbon in the type i biosphere, 5i the total produc- tween the spread of biosphere, increased silicate weathering, tivity of the type i biosphere, and τker is the residence time and a consequent cooling of the climate. of carbon in the kerogen. The accretion ratio, A, is defined The main questions to be answered in the following are: as the fraction of seafloor carbonates accreted to the conti- What are the life spans of the three different types of bio- nents to the total seafloor carbonates. The regassing ratio, sphere and what are the reasons for their extinction? R, is defined as the fraction of seafloor carbonates regassed into the mantle to the total subducting carbonates. SA and dm are calculated from a parameterized thermal evolution 2 Model description model of whole mantle convection including the water ex- change between mantle and surface reservoirs (Franck and The global carbon cycle model of Franck et al. (2002) de- Bounama, 1995). The box model including the pertinent scribes the evolution of the mass of carbon in the mantle, fluxes is sketched in Fig. 1. Cm, in the combined reservoir consisting of ocean and at- mosphere, Co+a, in the continental crust, Cc, in the ocean 2.1 Climate modelling crust and floor, Cf , in the kerogen, Cker, and in the differ- ent biospheres, Cbio,i(i=1, . , n), where n is the number In order to calculate the surface temperature, Ts, we need of the distinct parameterized biosphere types. The equations a climate model, which links the temperature to the given for the efficiency of carbon transport between reservoirs take partial pressure of atmospheric CO2 and the solar constant, into account mantle de- and regassing, carbonate precipita- S. We apply the grey atmosphere model of Lenton (2000). tion, carbonate accretion, evolution of continental biomass, The temperature is determined using energy balance between the storage of dead organic matter, and weathering processes. the incoming and outgoing radiation: dCm −1 4 (1 − a) S 3 = τ (1 − A) RCf − SA fc dm Cm/Vm (1) σ T = 1 + τ , (7) dt f s 4 4 where σ is the Stefan-Boltzmann constant, a is the aver- dC o+a = −1 − − + + age planetary albedo, and τ is the vertical opacity of the τf (1 A)(1 R) Cf SA fc dm Cm/Vm dt greenhouse atmosphere. The opacities of the two greenhouse n + + − X −1 + −1 − gases, CO2 and H2O, are assumed to be independent from Fweath (Co+a,Cc) (1 γ ) τbio,iCbio,i τker Cker i=1 each other: n X τ = τ pCO + τ pH O . (8) − 5i (Co+a) − Fprec (Co+a,Cc) − Fhyd (2) 2 2 i=1 The opacity of CO2 is assumed to be a function of its mix- ing ratio. It is derived from the results of varying CO2 in dCc −1 = τ AC − F (C + ,C ) (3) dt f f weath o a c a radiative-convective climate model (Kasting et al., 1993).
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